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Stylolites, Porosity, Depositional Texture, and Silicates in Chalk Facies Sediments

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Stylolites, Porosity, Depositional Texture, and Silicates in Chalk Facies Sediments Downloaded from orbit.dtu.dk on: Dec 19, 2017 Stylolites, porosity, depositional texture, and silicates in chalk facies sediments Ontong Java Plateau - Gorm and Tyra fields, North Sea Fabricius, Ida Lykke; Borre, Mai K. Published in: Sedimentology Link to article, DOI: 10.1111/j.1365-3091.2006.00828.x Publication date: 2007 Link back to DTU Orbit Citation (APA): Fabricius, I. L., & Borre, M. K. (2007). Stylolites, porosity, depositional texture, and silicates in chalk facies sediments: Ontong Java Plateau - Gorm and Tyra fields, North Sea. Sedimentology, 54, 183-205. DOI: 10.1111/j.1365-3091.2006.00828.x General rights Copyright and moral rights for the publications made accessible in the public portal are retained by the authors and/or other copyright owners and it is a condition of accessing publications that users recognise and abide by the legal requirements associated with these rights. • Users may download and print one copy of any publication from the public portal for the purpose of private study or research. • You may not further distribute the material or use it for any profit-making activity or commercial gain • You may freely distribute the URL identifying the publication in the public portal If you believe that this document breaches copyright please contact us providing details, and we will remove access to the work immediately and investigate your claim. Sedimentology (2007) 54, 183–205 doi: 10.1111/j.1365-3091.2006.00828.x Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea IDA L. FABRICIUS and MAI K. BORRE1 Institute of Environment and Resources, Technical University of Denmark, Bygningstorvet 115, DK-2800 Kgs. Lyngby, Denmark (E-mail: [email protected]) ABSTRACT Comparison of chalk on the Ontong Java Plateau and chalk in the Central North Sea indicates that, whereas pressure dissolution is controlled by effective burial stress, pore-filling cementation is controlled by temperature. Effective burial stress is caused by the weight of all overlying water and sediments as counteracted by the pressure in the pore fluid, so the regional overpressure in the Central North Sea is one reason why the two localities have different relationships between temperature and effective burial stress. In the chalk of the Ontong Java Plateau the onset of calcite-silicate pressure dissolution around 490 m below sea floor (bsf) corresponds to an interval of waning porosity-decline, and even the occurrence of proper stylolites from 830 m bsf is accompanied by only minor porosity reduction. Because opal is present, the pore-water is relatively rich in Si which through the formation of Ca–silica complexes causes an apparent super-saturation of Ca and retards cementation. The onset of massive pore-filling cementation at 1100 m bsf may be controlled by the temperature-dependent transition from opal-CT to quartz. In the stylolite-bearing chalk of two wells in the Gorm and Tyra fields, the nannofossil matrix shows recrystallization but only minor pore-filling cement, whereas microfossils are cemented. Cementation in Gorm and Tyra is thus partial and has apparently not been retarded by opal-controlled pore-water. A possible explanation is that, due to the relatively high temperature, silica has equilibrated to quartz before the onset of pressure dissolution and thus, in this case, dissolution and precipitation of calcite have no lag. This temperature versus effective burial stress induced difference in diagenetic history is of particular relevance when exploring for hydrocarbons in normally pressured chalk, while most experience has been accumulated in the over-pressured chalk of the central North Sea. Keywords Cementation, chalk, diagenesis, North Sea, Ontong Java Plateau, porosity, stylolites. INTRODUCTION role (e.g. Scholle, 1977; Bathurst, 1995), but it remains an issue of debate how temperature and Cementation of chalk during burial diagenesis pressure controls this process, and whether clay requires a source of carbonate and it is generally minerals promote the process (e.g. Heald, 1955; accepted that pressure dissolution plays a major Simpson, 1985; Lind, 1993a; Sheldon et al., 2003; Safaricz & Davison, 2005). It also remains unclear 1Present address: Mærsk Olie og Gas A/S, Copen- how diagenetically controlled changes in the hagen, Denmark. mineralogy of silicates in the chalk influence Ó 2006 The Authors. Journal compilation Ó 2006 International Association of Sedimentologists 183 184 I. L. Fabricius and M. K. Borre changes in the dominating carbonate phase SAMPLES AND METHODS (Baker et al., 1980; Hobert & Wetzel, 1989). Finally presence of hydrocarbons may have an Ontong Java Plateau influence on the diagenetic process (Scholle, 1977). Ooze and chalk with colour bands as well as Diagenetic processes are controlled by tem- chalk and limestone with stylolites were sampled perature, burial stress and pore-pressure, so, by from Site 807 during ODP Leg 130 (Fig. 1). Part of comparing two settings where some but not all each sample was impregnated with epoxy resin of these conditions differ, the understanding of and polished before backscatter electron micro- chalk diagenesis and porosity development graphy using a Philips XL40 scanning electron during burial should be improved. The two microscope (Philips, Holland). Silica and barite settings are the chalk facies sediments and were analysed by wavelength dispersive micro- sedimentary rocks of the Ontong Java probe analysis using a JEOL Superprobe 733 Plateau as found in Ocean Drilling Program (JEOL, Japan). Standards were: quartz, barite, (ODP) Leg 130 Site 807 (no hydrocarbons) and celestite, and calcite. chalk of the Central North Sea as found in two Another part of each sample was soaked in wells of the Gorm and Tyra fields (hydrocarbon demineralized water and slowly leached by acetic bearing). acid, while controlling the pH to be above 5Æ5in The main components of pelagic chalk are order to prevent dissolution of all non-carbonates. calcareous nannofossils and microfossils. Due to The filtrate was analysed for Al, Fe, Mg, Si, and Sr the contrast in size between these fossils, micro- by Atom Absorption Spectroscopy (Perkin-Elmer fossils reside in a continuous matrix of nanno- 5000, CT, USA). The residue was analysed for fossils. In the North Sea area, chalk facies mineralogical composition by X-ray diffraction by sediments of the Upper Cretaceous and Palaeo- use of Cu K-a radiation over an interval of 2Q 2° to gene Chalk Group are commonly referred to as 60°. Diffractograms were also recorded from 2° to ‘chalk’ irrespective of degree of induration. This 30° subsequent to 3 days of glycolation at 60 °C, may cause confusion when comparison is made and subsequent to heating to 300 °C and to 500 °C to pelagic deep sea carbonate sediments. These respectively in order to identify clay minerals. sediments and sedimentary rocks of Cretaceous Image analysis was done on backscatter elec- to Present age are of chalk facies and very tron micrographs of impregnated polished sam- similar in appearance and composition to North ples also studied by Borre & Fabricius (1998), to Sea chalk, but they are described as carbonate measure nannofossil matrix porosity, and ooze, chalk or limestone as a reflection of amounts of large particles (e.g. foraminifers) and increasing induration (Mazzullo et al., 1988). In pores by use of the filtering method described by the discussion of diagenesis a distinction is Borre (1997; Figs 2 and 3). Samples, visually free made between recrystallization and pore-filling of stylolites or colour bands, were analysed for cementation. Recrystallization involves local specific surface area using N2 adsorption (BET) simultaneous dissolution of carbonate particles with a MicromeriticsGemini III 2375 surface area and overgrowth on carbonate particles, where no analyser (GA, USA). 2+ 2À net transport of Ca and CO3 is required and no porosity change necessarily is involved, Gorm and Tyra fields whereas pore-filling cementation is a result of diffusion and net precipitation of material Plug samples from Gorm Field well N-22X and derived, e.g. from dissolution at stylolites (Borre Tyra Field well E-5X (Fig. 1) were chosen, so that & Fabricius, 1998). for most samples He-porosity data were available The present paper includes a discussion of the from the operator. Ultrasonic velocity data of the role of temperature and stress on stylolite forma- samples were discussed by Borre (1998). The tion, and the role of clay minerals in pressure majority of the Gorm Field samples were dis- dissolution. It also discusses the mainly porosity- cussed with respect to specific surface and per- neutral process of recrystallization, as well as meability by Mortensen et al. (1998). The Tyra pore-filling cementation, and how these processes samples were discussed with respect to image are related to depositional texture and the non- analysis by Røgen et al. (2001), and with respect carbonate components of the chalk. Finally the to permeability and capillary entry pressure by effect of these processes on porosity and perme- Røgen & Fabricius (2002). In the present study ability is discussed. backscatter electron micrographs from all se- Ó 2006 The Authors. Journal compilation Ó 2006 International Association of Sedimentologists, Sedimentology, 54, 183–205 Stylolites in Ontong Java Plateau chalk and North Sea chalk 185 Fig. 1. Location of studied wells: The Ontong Java Plateau, Ocean Drilling Program Leg 130, Site 807, Gorm Field well N-22X, and Tyra Field well E-5X (modified after http://www-odp.tamu.edu/sitemap/ sitemap.html). lected samples were analysed to measure matrix large pores (Fig. 3; Bachman, 1984). Below porosity and amount of large particles and pores 1135 m below sea floor (bsf) in the limestone by use of the filtering method described by Borre interval, several beds of re-deposited sediment (1997; Fig. 3); and to measure specific surface by were recorded, as indicated by intra-clasts, silicate use of the filtering method described by Borre clasts, and slump structures (Kroenke et al., 1991).
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